Field report of malakand field trip ,geology department university of peshawar

1. 1
FIELD REPORT OF MALAKAND FIELD TRIP
SUPERVISORS:
• MR.NAVEED ANJUM
SUBMITTED TO:
• MR.NAVEED ANJUM
SUBMITTED BY:
• MUHAMMAD SULIMAN
BS GEOLOGY PART: 1st
UOP PESHAWAR

2. 2
Table of Contents
Abstract …………………………………………………………………i
Introduction …………………………………………………………..ii
Lacustrine fluvial deposits..........................................1
Metasedimentary rocks .............................................2
a)Graphitic schist
b)Talc-mica-schist
c) Quartz-mica-schist
d)Green schist
e)Garnet-mica-schist
f) Banded marble
Igneous rocks.............................................................3
a)Malakand granite
Geological structures .................................................4
Dykes:
b)Sedimentary dyke
c) Amphibolite dyke

3. 3
Petrogenetic studies of the Malakand Granite, Metasedimentary complex,
banded Marble and Jalala lacusterian fluvial deposits are carried out. The
metasediments and Gneisses generally indicate a green schist facies
metamorphism which locally near the contact of Malakand Granite, are
metamorphosed up to the Garnet zone of the amphibolite facies. In Malakand
Granite, biotite, amphibole and opaque ore have crystallized at a temperature
grater than 875c and pH2o of grater than 5Kb. Following Muscovite plagioclase
has developed at a temperature grater of 800-850 degree c and pH2o less than
5kb and crystallization has occurred at 700c under PH2O less than 5kb.the
dominant fractionation was of plagioclase on the liquidus. On the basis of age,
geochemistry and grade metamorphism the Malakand Granite does not seems
to be part of alkaline igneous province.

4. 4
Our 3rd
geological trip was arranged on 02/05/2019 to the area of Malakand
along with Jalala lacusterian fluvial deposits. The trip was organized under the
supervision of MR.NAVEED ANJUM.
We left the department at 8:30 am sharply, and started our journey through
Motorway from Peshawar to Malakand passing through Charsadda district.
The Peshawar basin is overlain by lacustrine sediments of quaternary age,
having maximum thickness of 300 meters.
It is imagined that Peshawar basin was bounded by mountains from all three
sides, except at south, the waters were flowing in from south, forming a lake
environment, due to uplifting of Attock-Cherat range, the basin came into
existence.
The Peshawar basin is bounded on the east by Gandghar range and river Indus,
on west by Khyber range and on north by rocks of lower Swat-Buner schistose
group (Ambela granitic complex). To the south of Peshawar basin is Attock-
cherat range.

5. 5

6. 6
Malakand Granite is one of the well known Granits of the North western
Himalayas occurring at longitude 34-36E and longitude 71-52 N along the main
Mardan-Swat road. It has intruded into Gneisses and Metasediments, possibly
Cambrian and Precambrian age, respectively. These rock crop out extensively
in Mountain surrounding the estern Peshawar basin and the Himalayan
foothills of swat district to the North. The area is composed of completely
deformed Paleozoic to Mesozoic shelf and platform, metasedimentary rocks
include pelitic, psammitic, calcareous and graphitic litholigies. The style and
metamorphism varies considerably across this belt.

7. 7

8. 8
We have studied lacustrine fluvial deposits and different lithology at Malakand
field which are given below…
 lacustrine fluvial deposits
 Graphitic schist
 Talc schist
 Quartz mica schist
 Green schist
 Garnet mica schist
 Banded Marble
 Malakand Granite
 Dykes
At the end of our field we returned back to Peshawar through Moterway.

9. 9
STATION 1:
Lacustrine; of relating to, or associated to lakes. Fluvial; of or found in river.
Lacustrine deposits: Sediments which are deposited in lakes is called lacustrine
deposits.
Fluvial deposits: Sediments which are deposited In running water (river or
steam) is called fluvial deposits.
It is imagined that Peshawar basin was bounded by mountains from all three
sides, except at south, the waters were flowing in from North to south, forming
a lake environment, due to uplifting of Attock-Cherrat range, the basin came
into existence. Repeatedly the area of Jalala was converted into lake and river
uplifting of Attock-Cherrat range and climatic changes. Thus two types of beds
were form, thin beds (by lake) and thick beds (by river).
At station 1 we have taken out of the Bus at the area of Jalala by our supervisor
to study lacustrine fluvial deposits of Jalala. We studied lacustrine fluvial
deposits at side of the road near Jalala bridge. Those deposit were consist of
two types of beds, clay beds and sand beds. The sand beds (mostly sand) were
deposited by river or
stream, called fluvial
deposits. In sand beds
gradation were present.
clay beds were mostly
consist of clay and silt
size sediments, which
were deposited in still
water of lake under the
action of gravity.
Dykes were also present
in Jalala deposits. One
possible explanation for Figure 1-fluvio lacustrine deposits of Jalala.

10. 10
those dykes is, that there were many joints present, later on these joints were
filled up with sediments and then lithified as a result dykes were formed. And
the 2nd
possible explanation is, during Himalayan orogeny differential stresses
were applied on these sediments from both sides, the water was squeezed out
and compacted as a result dykes were formed.
Lacustrine deposits: thin beds mostly of clay and silt
Fluvial deposits: thick beds mostly of sand and silt.
STATION 2:
Graphitic Schist of the Malakand pass near Dargai village is the part of Alpuri
Group of Swat-Buner (well exposed in Swat-Buner). Alpuri group consist of four
formations namely
1. Nikanai Ghar formation
2. Saidu formation
3. Kashala formation
4. Marghazar formation. The schistose rocks following the limestone blocks
between Malakand
proper and road
tunnel contained
markedly high
proportion of
graphite. The rocks
is greyish black to
black in color. It
can be
distinguished from
green schist on the
basis of high
amount of total
mica and graphite
Figure 2-Vein in graphitic schist of Malakand pass.

11. 11
and a lower chlorite content. On the other hand we can also distinguish
graphitic schist from green schist by the property of imparting black
color to finger when rubbed on it surface. Graphite occur in the form of
layers, streaks and films along the schistosity plan.
Quartz veins were present in graphitic Schist, perpendicular to the bedding
plain.
Minerology: The
graphitic schist of
Malakand pass
contains graphite,
quartz, muscovite,
and biotite as major
constituents.
Color: greyish black
to black.
Wavy surface: The
surface of graphitic
Schist have wavy like
appearance.
Protolith: the
protolith of graphitic
schist is carbonaceous shale.
Silky luster: Shining due to presence of graphite.
Figure 3-graphitic schist of Malakand pass.

12. 12
STATION 3A:
After studing the Graphitic Schist we further moved to North where we
observed Talc schist. Graphitic schist near Dargai village was over lained by Talc
schist. Our supervisor told us, that touch these rocks by hand and tell me what
did you feel. When we touched those rocks, that given us greasy like touch. We
also scratched Talc Schist by our finger nail which confirmed that the hardness
of these rocks is less then that of finger nail (2.5). There were no shiny
appearance of
Talc schist which
confirmed that no
mica is present.
The protolith of
Talc Schist is
Danite and
peridotite or
impure limestone
(marl) which was
later on
metamorphosed
into Talc Schist.
Ferogenous
impurities was
present in Talc
Schist.
Lithology: Talc, muscovite,
Color: white to white grey.
Luster: earthy
Protolith: Danite and Peridotite or impure limestone (marl).
Figure 4-Talc schist of Malakand pass.

13. 13
STATION 3B:
A small north south trending schistose outcrop dominantly
composed of quartz and muscovite is exposed at the south of the tunnel.
Quartz-mica-schist is
consist of more then 60%
of mica, therefore the
surface of quartz-mica-
schist is producing more
shining.
The quartz-mica-schist is
dominantly composed of
muscovite and quartz.
Apatite opaque iron ore,
and epidote minor
constituents.
Iron leaching can be
noticed at the margins
and along at the
cleavages of these grains.
STATION 4A:
Schistose rocks near Malakand tunnel belong to this group.
They vary in color from light grey to dark grey. Amphibole, muscovite, biotite
and quartz can be identified in hand specimen. The rock is fined grained and
the schistosity is developed due to the parallel alignment of the micaceous
minerals and amphibole.
Intense deformation has been noticed in the green schist. Surface weathering
is common but the intensity of weathering increases towords the area of lower
attitude (i.e. toword Dargai in the south).
Figure 5-Quartz mica schist

14. 14
The green schist is fine to medium grained, and is dominantly composed of
amphibole, epidote,
quartz, and
plagioclase.
Chlorite, biotite,
sphene and opaque
ore are common
accessories.
The textural relation
of these minerals
indicate that
amphibole has
developed due
expences of
plagioclase and
opaque ore.
The green color of
the schist is due to the presence of minerals chlorite, epidote and actinolite.
Figure 6-green schist adjecent to Malakand tunnel

15. 15
STATION 4B:
We have studied Garnet-mica-schist near the north side of
Malakand tunnel. Isolated patches containing porphyroblasts have been
noticed in green schist on the road side adjacent to the Malakand tunnel. At
Malakand, Garnet grains varies from 0.7-1 cm across have been formed near
the contact of
Malakand tunnel in
Garnet-mica-schist.
Garnet-mica-schist
varies in color from
greenish to brown
and trends NE-SW.
the rocks are highly
weathered and show
iron leaching on the
surface. Garnet,
biotite, muscovite
and quartz can be
identified in hand
specimen.
The Garnet-mica-
schist of the Malakand tunnel (thermal aureole) contains, Garnet, muscovite,
biotite, quartz and alkalifeldspar as essential minerals while opaque ore,
chlorite, sphene and tourmaline occur as accessories. Garnet occur as
porphyroblasts while other mineral form the matrix. The development of
Garnet has been attributed to the reaction between biotite and muscovite.
Garnet developed normally at high temperature. This additional high
temperature was supplied by the intrusion of granitic magma of Malakand
granite.
Figure 7-garnet mica schist to North of Malakand tunnel.

16. 16
STATION 4C:
We observed banded Marble adjacent to the Malakand tunnel.
It was confirmed by our supervisor by putting dilute HCl on it surface, which
showed effervisence. The effervicence was due the reaction between HCL and
CaCO3, CO2 was released as bubbles.
HCL (dil) + CaCo3 = Co2(g)+ Ca + Cl
In this trip, field observation were made in the Malakand area. In this part of
sequence, some meter thick Marble layers, although decimeter to meter thick
amphibolite and
micaceous schist were
also found.
The protolith of the
banded Marble is
limestone. When
limestone of that area
was metamorphosed due
to Himalayan orogeny,
the fine grains of
limestone are converted
into course grained
Marble. Its grain size is
coarse, gives a sugary
texture. Honey comb like structure was observed on the weathered surface of
marble, and it’s a major feature of limestone to differentiate from quartz
sandstone. The bedding was 1-3cm thick.
Figure 8-marble in mouth of tunnel

17. 17
STATION 5:
The Malakand granite is roughly an oval shaped body, covering
about 40 sq. km area, intruding into and granite gneiss of probably
Precambrian age.
It is locally porphyritic, course to fine grained, and dominantly medium grained
rock with a hypidiomorphic to allotriomorphic texture. Near the contact the
main granitic body is relatively fine grained, however patches and intrusion of
fine grained material can also be noticed with in the main body of granite. The
color varies from white on fresh surface to brown and brownish black at
weathered surface.
In hand specimen muscovite, biotite, quartz, plagioclase and alkali feldspar can
be identified.
The typical granite joint system with well defined rift and grains is wide spread
in granite. Later feldspar rich pegmatitic and aplitic veins normally follows
these joints. Granite is normally fined grained.
Evidence of intrusive
relationship of granite both
with metasediments and
gneisses have been noticed
at several localities. For
example at Malakand the
granite and metasediments
have a sharp contact and
granite veins intrude the
metasediments near the
contact.
Beside, garnet has
developed due to the
thermal effect of granite of
metasediments near the
contact at Malakand
Figure 9-pegmatite in malakand Granite at Malakand top

18. 18
tunnel. Pegmatite were also studied in Malakand geanite.
STATION 1:
DYKE: Dikes are sheet intrusions that cut across layers, or into an unlayered
mass. Dikes usually follow zones of weakness in the rocks they travel through.
Even if they came to lie horizontal, for example by folding, as long as they cut
host rock strata they are still dikes. The rocks in dikes can be both pegmatites
(very coarse-grained) and aplites (sugary fine-grained). Several dikes together
can form a dike swarm. – In scientific terms, a dike is a relatively narrow
tabular discordant body which propagates through rock perpendicular to the
least principal stress.
We observed dykes in Jalala deposits. Those were intruded the sedimentary
beds of clay and sand deposit beds alternately. One possible explanation for
those dykes is, that
there were many joints
present, later on these
joints were filled up
with sediments and
then lithified as a result
dykes were formed.
And the 2nd
possible
explanation is, during
Himalayan orogeny
differential stresses
were applied on these
sediments from both
sides, the water was
squeezed out and
compacted as a result
dykes were formed.
Figure 10-dyke in sedimentary deposits of Jalala

19. 19
STATION 4D:
Dikes are sheet intrusions that cut across layers, or into an
unlayered mass. Dikes usually follow zones of weakness in the rocks they travel
through. Even if they came to lie horizontal, for example by folding, as long as
they cut host rock strata they are still dikes.
On the right side of the Malakand tunnel we observed amphibolite dyke. The
dyke cutted up perpendicularly the schistose rocks of that area. Protolith of
the amphibolite
dyke is gabbro,
which was later on
due to Himalayan
orogeny
metamorphosed
into amphibolite.
The dyke is older
then the processes
of metamorphism
because the dyke
cross cutted up the
country rocks and
later on this whole
lithology with dyke
was
metamorphosed.
Protolith: gabbroic
rocks
Color: green to black
Lithology: amphibolite
Area: Malakand pass, right side of the tunnel.
Figure 11-amphibolite dyke in schistose rocks of malakand

20. 20
 Paper of M. Qasim Jan, Ikhlaq Ahmad Bhatt and Noor Jeha
Metamorphic mineral assemblages south of the Malakand and adjoining
areas, northern Pakistan.
 Sir Naveed Anjum lectures / notes
 Physical geology by c.c plummer